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Chromite Oxidation Patterns Associated to Serpentinization: Case Studies from the Mid-Atlantic Ridge, the Alter do Chão Massif (NE Alentejo, Portugal) and the Ronda Massif (Spain)
Received: 10 August 2022 / Revised: 6 October 2022 / Accepted: 11 October 2022 / Published: 15 October 2022
Chromite oxidation in the serpentinization of host peridotites is a well-documented process. The detailed technical data of chromites and Cr-rich spinels from three geotectonic settings provided the basis for this study, focusing on the comparison of their chemical properties as a way to evaluate the movement of spinel groups during the serpentinization in those different conditions, namely: (i) aggravation of the upper ocean coast in the Azores area of the Mid-Atlantic Ridge (MAR); (ii) serpentinized peridotite from Cabeço de Vide (CV, Alter do Chão Massif, Portugal); and (iii) serpentinized subcontinental mantle peridotite from the Ronda Massif (Spain). Electron microprobe data show that: (i) regardless of geotectonic setting and initial formation, Cr-spinels follow four processes similar diseases; (ii) rapid Cr-spinel oxidation, including Mg- and Al-depletion important to lead to the formation of ferritchromit rims, is more intense in CV serpentinites than in MAR and Ronda serpentinites nearby from; (iii) except for Zn, the investigated elements (Mn, Ti, V, Ni and Co) appear to be immobile during oxidation. the bone, and slightly enriched with ferritchromit rims; (iv) severe magnetization of Cr-spinel is responsible for the incomplete outer magnetic field on many grains. Time, water pH, and water/rock ratio appear to be the main factors that control the intensity and extent of chromite oxidation.
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, ± Zn, Ni, Co), and B refers to the octahedral site, which is usually occupied by trivalent transition metal cations (Al, Cr, Fe.
, ±Ti, V) [1, 2]. In magnesiochromites and chromites, Cr is the main cation in the B position, while in chromian spinels, Al dominates that position [1, 2]. The term “chromite” is often used in the literature in a general sense, including the three populations of Cr-rich oxyspinels that were the subject of this study. The name “ferritchromit”, following its original definition, is used exclusively to refer to F
Enriched chromite is caused by the oxidation of original chromites, so the name has both a creative meaning and a meaning.
Chromites or chromian spinels are common in peridotitic rocks, and their oxidation during serpentinization of peridotites, with the formation of ferritchromite (± magnetite) rims in on the primary chromite grains, due to the gradual deposition of Fe.
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And strong Mg, Al, and finally, Cr, reduction, has been recorded for many events [3, 4, 5, 6, 7, 8, 9, 10, 11, 12]. The amount of magnetite produced as a result of the oxidation of chromite is usually insignificant compared to the secondary magnetite that results from the serpentinization of olivine (± pyroxene) in these rocks.
Most of these studies have also discussed the origin of ferritchromit (± magnetite) as products of chromite alteration or accretion on the original chromite, taking into account both the rate of diffusion of Mg , Al, Fe and Cr, and their solubilities under different pH conditions [3, 4]. As far as we know, however, studies on the use of chromite oxidation rate to control the ratio of elements in different disease states and under the interaction of different chemicals have not been published. The evaluation of such differences has been the focus of the present study, based on the analytical data collected for chromite-ferritchromit bands in serpentinites from three different geotectonic areas, namely the Azores part of the Mid-Atlantic Ridge (MAR), the Alter do Chão mafic. -ultramafic massif (NE Alentejo, Portugal), and the Ronda peridotite massif (SW Spain), and on the information found in the literature about the serpentinizing fluids in each case.
The first studies in the MAR serpentinites [13, 14, 15] and the detailed description of the Alter do Chão and Ronda serpentinites show that the relic chromite is everywhere and some olivine (more rarely orthopyroxene) can still be seen in some of these rocks, no matter what. their degree of marine or the size of the snake.
Specimen data for the abundance of chromite and Cr-rich spinel grains (a total of 93 grains) from snakes collected at these three sites are presented and discussed. below. Special emphasis is placed on the comparative discussion of the movements of the main chemical groups of chromite, during its oxidation, and how it is formed. the oxidation of chromite at each site.
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The first results of this study are about how water chemistry and physical properties control the movement patterns of chromite particles in the time of the serpentinization of its host-rock, can be a useful method not only in future studies about the serpentinization of chromite-bearing ultramafic rocks, but also in research analysis of ultramafic-hosted ores.
Three sets of chromite-bearing serpentinized peridotites from different geological settings were used in the present study. Their geotectonic conditions are described below.
The larger peridotite set corresponds to chromite-bearing harzburgite from the Rainbow hydrothermal field (36°14′ N) [16, 17, 18, 19] and from the Saldanha site (36°34′ N) [20, 21, 22, 23], in the Azores part of the MAR (Figure 1a). These two areas are located on parts of the second ridge that are connected by the left side that does not change faults, under the thermal and chemical stress of the Azores hotspot [16]. This area enjoys deep sea flow and provides evidence of recent evolution and subsequent tectonic uplift and exposure of the uppermost serpentine string of ultramafics on the ocean floor, a constant phenomenon on the MAR and other slow-spreading ridges is characterized by limited melt production and long-term tectonics. addition [22, 24, 25, 26, 27, 28, 29, 30]. Previous mineralogical and isotopic analyzes of these MAR serpentinites indicate that: (i) the serpentine formed at temperatures below 300–200 °C; (ii) in addition to a lot of rock fluid and some large parts lost, the coast also includes a lot of oxidation, with a big increase in Fe-rock as a whole .
The CV chromite set was sampled in serpentinized dunites and harzburgites from Cabeço de Vide, at the SW end of the Alter do Chão Mafic-Ultramafic Massif, NE Alentejo (Portugal; Figure 1b). The Alter do Chão pluton consists of gabbroic rocks and serpentinized peridotite, and interrupts the thick Elvas Cambrian carbonate sequence, producing a strong metamorphic aureole on the contact zone [31]. The gabbroic rocks are probably older than the ultramafic rocks and correspond to more than one event. The ultramafic rocks include peridotites, dunites and pyroxenites, showing variable degrees of serpentinization [ 31 , 32 , 33 , 34 ]. Although the pluton and its rocks are affected by many effects of Hercynian metamorphism low to intermediate-grade, as well as many metasomatic effects (serpentinization, amphibolitization, scapolitization), the CV serpentinites and groups serpentinized peridotites exposed. no obvious signs of plastic degradation or sampled disease in thin section; The loss of olivine, on the other hand, has been very strong and may have enhanced the water flow and corrosion of these peridotites.
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Figure 1. Location of the study areas: (a) Rainbow and Saldanha hydrothermal areas, in the Azores area of the Mid-Atlantic Ridge [18, 20]; (b) AC1 and AC2 pits (secret by A. Cavaco Co.), in the village of Cabeço de Vide, in the Alter do Chão mafic-ultramafic massif, NE Alentejo, Portugal (cited [31]); (c) the Bermeja Formation of the Ronda Massif in the Betic Cordillera, SW Spain (adapted from [35]).
In the serpentine peridotite of Alter do Chão, there are more pseudomorphic textures, probably due to the low water/rock and/or limited tectonic deformation than those in.
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